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Monday, 30 June 2014

The accident of the Fukushima Dai-ichi nuclear power plant in March 2011
released a large amount of radiocesium into the North Pacific Ocean.
Vertical distributions of Fukushima-derived radiocesium were measured at
stations along the 149°E meridian in the western North Pacific during
the winter of 2012. In the subtropical region, to the south of the
Kuroshio Extension, we found a subsurface radiocesium maximum at a depth
of about 300 m. It is concluded that atmospheric-deposited radiocesium
south of the Kuroshio Extension just after the accident had been
transported not only eastward along with surface currents but also
southward due to formation/subduction of subtropical mode waters within
about 10 months after the accident. The total amount of decay-corrected 134Cs in the mode water was an estimated about 6 PBq corresponding to 10–60% of the total inventory of Fukushima-derived 134Cs in the North Pacific Ocean.

The massive Tohoku earthquake and consequent giant tsunamis on 11
March 2011 resulted in serious damage to the Fukushima Dai-ichi nuclear
power plant (FNPP1)1. Radiocesium (134Cs and 137Cs) derived from the damaged FNPP1 caused radioactive contamination of the islands of Japan and the North Pacific Ocean2.
Most of the Fukushima-derived radiocesium deposited on land has
remained in soils. Within about 100 km of the FNPP1, where contamination
was serious, the radiocesium in soils has been measured intensively3. The decay-corrected ratio of 134Cs/137Cs in soils has been calculated to be 1.0, which suggests that the total amounts of 134Cs and 137Cs
released from FNPP1 were equivalent. The relationship between the
radiocesium activity in the soil and the air dose rate derived from
airborne monitoring has provided a map of the density of radiocesium
deposition throughout the islands of Japan4. The sum of the deposition, the total inventory of 137Cs (or 134Cs) on the islands of Japan, has been estimated to be 2.4 PBq5.
However, the total amount of Fukushima-derived radiocesium in the North
Pacific remains uncertain, because it has been difficult to obtain
sufficient samples of water, especially from subsurface and deep waters,
in the vast North Pacific Ocean, except from the coastal area near the
FNPP16, 7, 8.
Radiocesium
isotopes were released into the North Pacific through two major
pathways, direct discharges of radioactive water and atmospheric
deposition. About ten days after the earthquake, Tokyo Electric Power
Company and the Ministry of Education, Culture, Sports, Science and
Technology of Japan (MEXT) began marine monitoring in the coastal area
within about 50 km from the FNPP16, 7, 8.
These high-frequency measurements have facilitated an evaluation of the
total amount of radiocesium derived from the directly discharged
radioactive water. The values estimated in several studies were in the
range 4–6 PBq1, 9, 10, 11, 12, 13, although one study calculated the value to be 27 PBq (12–41 PBq)14. The total direct release of 27 PBq was somewhat of an overestimate11, 15 and resulted in activities in a model ocean that were unrealistically high compared to activities measured in the real ocean16. However, radiocesium activities measured during a cruise in June 2011, mainly in the open ocean17, indicated that the total activity of 137Cs (or 134Cs) directly discharged to the ocean equaled 11–16 PBq18, 19.
A
large portion of the radiocesium released to the atmosphere from the
FNPP1 was deposited onto the North Pacific Ocean, because the winds over
Japan usually blow from the west in the spring20.
However, the small number of observational data in the open ocean
cannot estimate the total oceanic deposition directly. Alternatively,
that could be calculated indirectly from the total amount of radiocesium
released to the atmosphere, which was derived primarily from
measurements on land. Estimations of the total amount released to the
atmosphere range widely, from 8.8 to 37 PBq1, 5, 9, 11, 14, 21, 22, 23, 24, 25.
The 2.4 PBq deposited onto the islands of Japan suggests that most of
the remaining radiocesium, 6.4–35 PBq, found its way into the North
Pacific through atmospheric deposition. Atmospheric models have
estimated independently the total oceanic deposition to be 5.8–30 PBq5, 9, 11, 12, 23, 25, similar to the range of 6.4–35 PBq. However, the deposition on land has been overestimated in many of the models.
Efforts
to obtain observational data from the open ocean have continued. The
marine monitoring from March 2011 by MEXT or the Nuclear Regulation
Authority was extended eastward to the 144°E meridian in August 20117. Radiocesium measurements in the area further east have been reported in several publications8, 17, 26, 27, 28, 29, 30, 31. Seawater sampling from April 2011 during commercial ship cruises has produced a valuable dataset across the North Pacific28,
although as in many other previous studies, most of the samples were
collected only at the surface. In June 2011 vertical profiles of the
Fukushima-derived radiocesium were measured at stations along 147°E
between 34.5°N and 38°N, and it was found that the radiocesium had
penetrated to a depth of about 200 m roughly two months after the
disaster17.
Although these observational data are still insufficient for direct
estimation of the total amount of radiocesium in the whole North
Pacific, these data can be used to validate ocean model simulations that
have predicted vertical and horizontal spreading of the radiocesium in
the ocean13, 15, 16, 25, 32, 33.
Here
we report the vertical distributions of the Fukushima-derived
radiocesium at stations along 149°E between 10°N and 42°N in the winter
of 2012, about ten months after the accident. Our preliminary reports,
which have already been published31, 34,
revealed that (1) the Fukushima-derived radiocesium activity was
highest in the transition area between the subarctic and subtropical
regions and (2) the radiocesium was transported southward across the
Kuroshio Extension (KE) through subsurface layers. In this study, we
discuss the causes of the southward spreading of the radiocesium based
on temporal changes in the activity of surface waters. Secondly, we have
estimated the vertical water-column inventory of radiocesium. These
results will contribute to determination of the total inventory of
radiocesium and will facilitate prediction of the spreading of the
Fukushima-derived radiocesium in the North Pacific Ocean in the future.
We measured both 134Cs and 137Cs activities (Methods). The ratio of decay-corrected 134Cs/137Cs in samples in which the 137Cs activity was higher than 20 Bq m−3 was about 0.95. The small excess of 137Cs was derived from another source of 137Cs, global fallout due to the nuclear bomb testing in the 1950s and 1960s35. The excess 137Cs in surface waters (about 1.5 Bq m−3) in the winter of 2012 corresponds to bomb-produced 137Cs activities (about 1.9 Bq m−3) in surface water of the North Pacific before the accident (about 2.4 Bq m−3 in 2000)36. Therefore, only results for 134Cs, which is a unique tracer of the FNPP1 accident, are presented in later sections.

Temporal changes in 134Cs activity in surface waters
Our
sampling stations were located in the western North Pacific from cold
subarctic to warm tropical regions, although information on sea surface
temperatures estimated by satellite sensors was patchy in the northern
area due to cloudy conditions during the sampling cruise (Figure 1a).
The image of sea surface height (SSH) implied that our observational
line along 149°E crossed eastward-flowing currents around 35°N and 40°N
where SSH gradient was relatively steep (Figure 1b).
The northern and southern currents correspond to the subarctic and KE
fronts, respectively. Here we define areas north of the subarctic and
south of the KE fronts as the subarctic and subtropical regions,
respectively. In addition, we designate the area between the two fronts
as the transition area, in which the FNPP1 is situated (Figure 1). Although a boundary between the subtropical and tropical regions is not clear in Figure 1, we provisionally regarded the area south of 20°N as the tropical region because of the subtropical front around 20°N37.
The distribution of SSH also suggests that the observational line
crossed a southward meander of the KE front around 148°E (A in Figure 1b).Figure 1: Water sampling locations for radiocesium
measurements superimposed on backgrounds of (a) sea surface temperature
(SST, °C) and (b) sea surface height (SSH, cm)

White and black circles denote stations for surface sampling only and a
deep hydrocast to a depth of 800 m, respectively. The red cross shows
the location of the Fukushima Dai-ichi nuclear power plant. The SST was
derived from Moderate Resolution Imaging Spectroradiometer data averaged
between 15 January 2012 and 14 February 2012 (Level-3, Terra, 4-km
resolution). The images of SST were produced by the Colorado Center for
Astrodynamics Research Data Viewer. The SSH map is based on one-week
average gridded data (1/3° × 1/3°) for 1 February 2012; they were
produced by the Segment Sol Multimissions d'Altimétrie d'Orbitographie
et de Localisation Précise/Data Unification and Altimeter Combination
System and distributed by the Archiving, Validation and Interpretation
of Satellites Oceanographic Data with support from the Centre National
d'Etudes Spatiales. The maps in this figure were drawn using Ocean Data
View54.

In surface seawaters, Fukushima-derived 134Cs activity was
detected at all the stations along the 149°E meridian from the subarctic
to tropical regions in the winter of 2012 (Figure 2). The radioactivity was highest (10–20 Bq m−3)
in the transition area between 35°N and 40°N. In the subarctic region,
north of 40°N, the activity decreased sharply at higher latitudes and
fell to about 0.2 Bq m−3 at the northernmost station. To the south of the KE, between approximately 30°N and 35°N, the activity declined to a few Bq m−3 and then dropped to less than 1 Bq m−3
farther south of 30°N. We also collected seawater samples along a zonal
transect at approximately 35°N, which crossed the southward meander of
the KE (A in Figure 1b). Relatively high activity (about 8 Bq m−3) was observed at a station at 148°E, near the approximate center of the meander.

Figure 2: 134Cs activity (Bq m−3) in surface seawaters of the western North Pacific from April 2011 to September 2012.

The activity was corrected to the date of sampling. Pink, red, yellow,
green, and blue symbols denote the activities in April–May 2011,
June–August 2011, September–December 2011, January–March 2012, and
April–September 2012, respectively. The data are from Honda et al. (2012)26 (diamonds), Buesseler et al. (2012)17(squares), Karasev (2012)27 (stars), Aoyama et al. (2013)28 (triangles), Kaeriyama et al. (2013)29 (inverted-triangles), Kamenik et al. (2013)30 (crosses), and this work (circles). Symbols without an error bar show the detection limits of analyses; their 134Cs
activities were less than the detection limit. Dots and the shaded area
on the map show the sampling locations of this work in the winter of
2012 and the area between approximately 145°E and 152°E sampled during
previous studies, respectively. The map in this figure were drawn using
Ocean Data View54.

To discuss temporal changes in the surface 134Cs activity, we also show in Figure 2 the activities measured in surface waters (0–20 m depth) between approximately 145°E and 152°E during previous studies17, 26, 27, 28, 29, 30.
Just after the accident, in April–May 2011, the activities between 30°N
and 40°N were high, though the range of activity was large
(approximately 2–1000 Bq m−3). In the transition area
(35°N–40°N), the activity increased significantly in the following
period, June–August 2011. After that time, the activity decreased
piecemeal and then fell to a few Bq m−3 in August 2012. The
surface activity in the subarctic region to the north of 40°N also
decreased monotonically from about 50 to a few Bq m−3 between
June 2011 and August 2012. The transitory increase during June–August
2011, which was observed in the transition area, was indistinct in the
subarctic region because of a lack of data in April–May 2011. To the
south of the KE, between 30°N and 35°N, the high surface activity in
April–May 2011 quickly decreased to a few Bq m−3 by June
2011. The magnitude of the temporal change of activity in the surface
waters to the south of 30°N, including the southern subtropical and
tropical regions, is uncertain, because 134Cs activity was detected only in the winter of 2012. 134Cs
has a short half-life of only 2.07 years, and the activity
decay-corrected to the sampling date decreased by 50–75% from April 2011
to September 2012. The fact that the observed activity decreased at a
rate faster than the radioactive decay rate suggests that the surface 134Cs activity was diluted by advection and diffusion.

Vertical profiles and inventories of 134Cs activity

In the transition area between 35°N and 40°N, where surface 134Cs activity was highest, 134Cs activity from the surface to a depth of about 200 m was almost constant (Figure 3a).
The homogeneity of the activity in the surface layer reflects surface
cooling and vertical mixing in the winter and is consistent with the
vertical uniformity of water temperature, salinity, density, and
therefore the small potential vorticity at that time (Figs. 3b–3e). The activity then decreased sharply just below the winter mixed layer. The 134Cs had penetrated to a depth of about 300 m by the winter of 2012. In the subarctic region, the 134Cs
activity in the surface mixed layer was also almost uniform vertically
but lower than in the transition area. The depth of penetration was
shallower than in the transition area, probably because the mixed layer
was shallower, about 150 m deep. At the northernmost station, the
activity in the mixed layer were lower as in the surface water. The
vertical profiles of 134Cs activity in the transition area
and subarctic region can be largely explained by vertical diffusion
between the surface mixed layer and deeper layers.

Contour intervals in (a), (b), (c), (d), and (e) are 2 Bq m−3, 1°C, 0.1, 0.2 kg m−3, and 5 × 10−11 m−1 s−1, respectively, except for broken (1 Bq m−3) and dotted (0.1 Bq m−3)
lines in (a). Dots show points sampled for radiocesium activity
measurements. Thick white lines in (b), (c), (d), and (e) indicate
isolines of 2 Bq m−3 of 134Cs activity. All data in this figure, except potential vorticity, are listed in Supplementary Table 1 together with the 137Cs data. This figure was drawn using Ocean Data View54.To the south of the KE, the surface activity was less than a few Bq m−3 in the winter of 2012 (Figure 2). Figure 3a indicates that the 134Cs
activity was also low (but significantly above the detection limit) in
the surface mixed layer from the surface to a depth of 150–200 m between
approximately 25°N and 35°N. In contrast, to the south of 20°N the
activity was not detected in the surface mixed layer to a depth of
100–150 m, except in surface waters collected with a bucket. Below the
surface mixed layer, we found a conspicuous subsurface maximum centered
at a depth of about 300 m throughout the subtropical region between 20°N
and 35°N. This subsurface tongue-shaped maximum appeared in a pycnostad
between potential density anomalies of approximately 25.0 and 25.6 σθ (Figure 3d), which corresponds to water temperatures of 15–18 °C (Figure 3b) and salinities of approximately 34.60–34.75 (Figure 3c). The pycnostad resulted in a subsurface minimum of potential vorticity (Figure 3e). Higher activities in the subsurface maximum were observed at 32°N and 34°N (10–20 Bq m−3), and the activity decreased at lower latitudes. We also note that the 134Cs had penetrated into deeper layers, to depths of at least 600 m, between 32°N and 35°N.
We calculated vertically integrated (i.e., areal) 134Cs inventories from the surface to a depth of 800 m in the winter of 2012 (Figure 4).
The areal inventories were corrected for radioactive decay to the date
of the earthquake, 11 March 2011. High areal inventories were observed
in the transition area, where surface activities were also high.
Although the surface activities were low in the subtropical region
between 30°N and 35°N, the areal inventories were comparable to those in
the transition area because of the subsurface activity maximum. The
areal inventories of 134Cs activity in the subarctic region
(40°N–42°N), transition area (35°N–40°N), and subtropical region
(20°N–35°N) were calculated to be 0.8 ± 0.1, 4.6 ± 0.3, and 1.6 ±
0.1 kBq m−2, respectively, where the error bounds indicate
standard deviations. We compared the areal inventories in the winter of
2012 with those calculated about 8 month earlier, in June 201117 (Figure 4). The areal inventory in the transition area (36°N–38°N) in June 2011, 7.9 ± 0.3 kBq m−2,
implies about a 40% decrease in the areal inventory between June 2011
and the winter of 2012, although the spatial variation in June 2011 was
larger than in the winter of 2012. The mean of the decay-corrected
radioactivity in the surface water also decreased by about 70%, from 73
to 21 Bq m−3, in the transition area during the same period. The higher rate of decline in the surface 134Cs
radioactivity was caused by its deeper penetration during the winter of
2012 (to a depth of about 300 m) than in June 2011 (to a depth of about
200 m). A relatively large areal inventory at the southernmost station
(36°N) to the south of the KE in June 2011 was caused by a subsurface 134Cs maximum at depths of 150–450 m.
Figure 4: Vertically integrated (areal) inventories of 134Cs (kBq m−2, right ordinate) in the western North Pacific.

Green and red histograms indicate inventories at the 15 stations along
approximately 149°E in the winter of 2012 and at 6 stations along 147°E
from 34°N to 38°N in June 201117, respectively. Error bars on the tops of histograms indicate uncertainties (standard deviations). The 134Cs activities (Bq m−3, left ordinate) in surface seawater in the winter of 2012 (green circles) and June 201117
(red squares) are also shown. The activities and inventories have been
corrected to 11 March 2011. The map in this figure were drawn using
Ocean Data View54.

In April–May 2011, just after the accident, the 134Cs activity was as high as 1000 Bq m−3
in the surface waters of the transition area and just to the south of
the KE (30°N–40°N) along approximately 145°E–152°E, more than 500 km
from the FNPP1 (Figure 2). In April 2011, 134Cs activity was also observed at stations in the subarctic and subtropical regions, more than 1000 km distant from the plant26, 28. The wide dispersal of Fukushima-derived 134Cs
in the western North Pacific within about two months of the accident is
consistent with patterns of atmospheric deposition of 134Cs simulated by atmospheric models13, 25, 38. A low-pressure system traveling across Japan from 14–15 March 2011 was found to be effective in lifting particles containing 134Cs
from the surface layer to the altitude of the westerly jet stream,
which carried the particles across the North Pacific within 3–4 days39.
In the transition area between 35°N and 40°N, the 134Cs activities in surface waters during June–August 2011 were significantly higher than in April–May 2011 (Figure 2),
which implied that contaminated waters discharged from the FNPP1 had
been transported by the eastward-flowing North Pacific Current (Figure 5).
The radiocesium activities in surface seawater collected by commercial
cruise ships revealed an eastward propagation of the main plume of the
directly discharged 134Cs. The zonal speed of the plume was estimated to be about 200 km month−1, a speed that was consistent with trajectories of Argo floats launched near the FNPP128. Therefore, arrival of the directly discharged 134Cs
water in June–August 2011 was delayed by about two months relative to
the atmospheric deposition in April–May 2011. The activity decrease in
September–December 2011 indicated that the main body of the plume had
passed to the east between April–May and September–December 2011. The
radiocesium, however, also had spread vertically and penetrated deeper
in the winter of 2012 (a depth of about 300 m) compared to June 2011 (a
depth of about 200 m).
Figure 5: A schematic view of formation and subduction of mode waters in the North Pacific.

Yellow and yellow-shaded ellipses indicate spreading and formation areas, respectively, of STMW (25.0–25.6 σθ). Green and green-shaded areas indicate spreading and formation areas, respectively, of CMW (26.0–26.6 σθ),
which is denser than STMW. Thick broken and solid arrows show spreading
directions of STMW and CMW, respectively. Blue and red dotted lines are
surface water currents of the subarctic and subtropical gyres,
respectively. The broken line denotes our observational line at 149°E in
the winter of 2012. SAF, KEF, and STF indicate the subarctic, Kuroshio
Extension, and subtropical fronts along the observational line,
respectively. The map in this figure were drawn using Ocean Data View54 and this figure has been modified from one in the literature55.The 134Cs activity in the subarctic region was lower than
in the transition area throughout the observational period; its pattern
of temporal change, however, was similar to that in the transition area (Figure 2). Whether there were intrusions of directly discharged 134Cs
from the transition area to the subarctic region is unclear, because
the transitory increase in June–August 2011 was obscure in the subarctic
region. Off the Kuril Islands, the activities in the surface waters of
the Oyashio Current, which flows into the subarctic region (Figure 5), were less than a few Bq m−3 in April 201127. If the supply of directly discharged 134Cs
to the subarctic region had been blocked by the subarctic front, the
surface activity in the subarctic region would have dropped more sharply
because of the inflow of Oyashio Current water, the 134Cs
activity of which was low. In fact, the low activity at the northernmost
station in the winter of 2012 implies an intrusion of Oyashio Current
water (Figure 3a). Therefore, it is likely that the directly discharged 134Cs
was transported into the subarctic region through water exchanges
between the transition area and the subarctic region. The gradual
decrease of surface 134Cs in the subarctic region indicates that the directly discharged 134Cs was transported eastward and diffused vertically over time, as was also the case in the transition area.
Between 30°N and 35°N in the subtropical region, the 134Cs derived from atmospheric deposition during April–May 2011 was apparently swept out in June–August 2011 (Figure 2). In May 2011, Fukushima-derived 134Cs was not detected in surface waters just south of Japan28, where the Kuroshio Current (the upper stream of the KE) flows northeastward (Figure 5). This low 134Cs
activity in the Kuroshio Current region suggests that a new and
relatively “clean” KE current from the west probably flushed out the 134Cs in the surface water between 30°N and 35°N. This process was also clearly demonstrated in ocean model simulations12, 13
and suggests that an exchange of surface seawater between the
transition area and the subtropical region was restrained by the KE
front. The 134Cs activity in the surface mixed layer between 25°N and 35°N was low but detectable in the winter of 2012 (Figure 3a). The 134Cs derived from atmospheric deposition just after the accident probably recirculated within the western subtropical region (Figure 5). Alternatively, the 134Cs in the mixed layer could be explained by entrainment of 134Cs from the subsurface maximum just below the mixed layer. To the south of 20°N, the 134Cs
was detected only in surface waters collected with a bucket. Although
the cause of those surface activities is not sure, a little
contamination on the bucket is possible.
In the subtropical region between 20°N and 35°N, we found a subsurface 134Cs maximum just below the surface mixed layer in the winter of 2012 (Figure 3a). This tongue-shaped subsurface plume appeared on a pycnostad between 25.0 and 25.6 σθ (Figure 3d) that resulted in a subsurface minimum of potential vorticity in the corresponding layers (Figure 3e). We conclude that the 134Cs subsurface maximum was derived from formation and subduction of Subtropical Mode Water (STMW)40. To the south of the KE between approximately 30°N and 35°N, STMW is formed and penetrates to a depth of about 400 m (25.6 σθ) in late winter. This STMW then spreads to nearly the subtropical front35 through advection over the Kuroshio recirculation region41, 42 (Figure 5). Atmospheric deposition of the Fukushima-derived 134Cs in the North Pacific Ocean occurred mainly in March 2011, when STMW was just being formed. Therefore, the 134Cs
deposited just to the south of the KE was probably mixed vertically to
depths of 300–400 m immediately. The high activities in the 134Cs subsurface plume at 32°N and 34°N (10–20 Bq m−3) were nearly identical with those in the surface waters between 30°N and 35°N in April–May 2011 (Figure 2). One could argue that the high subsurface activities in the winter of 2012 were remnants of the 134Cs that penetrated deeply during March 2011. The 134Cs in newly formed STMW then started to spread to around 20°N along subsurface isopycnals (25.0–25.6 σθ). In June–August 2011, the 134Cs
in the surface mixed layer between 30°N and 35°N may have been flushed
out and the subsurface plume appeared between 20°N and 35°N (Figure 3a). The subsurface maximum observed at 36°N to the south of the KE in June 201117 is consistent with the immediate subduction of the Fukushima-derived 134Cs.
The deeper penetration of 134Cs to depths of about 600 m (26.6 σθ) between 32°N and 35°N (Figure 3a) cannot be explained by formation of STMW, the deepest convection of which is to about 400 m (25.6 σθ). The penetration of the 134Cs to 26.0–26.6 σθ is reminiscent of ventilation of another, denser mode water in the North Pacific, the Central Mode Water (CMW)43.
The formation area of CMW is situated in the transition area in the
central North Pacific. The CMW spreads eastward along the North Pacific
Current, turns southward, and then turns westward (Figure 5). Despite its similar water density anomaly (26.0–26.6 σθ),
the path of the CMW as it spreads is likely to be to the south of
approximately 30°N, along 149°E. In addition, a transit time as short as
about 10 months (between March 2011 and January 2012) from the
formation area to 149°E longitude is not plausible, because the renewal
time of CMW is more than 20 years44.
Another possible explanation for the deeper penetration is conveyance of 134Cs
from the transition area across the KE. The satellite image of SSH
indicates that stations at 32°N and 34°N were located near a cyclonic
eddy centered at 33°N, 151°E (B in Figure 1b).
This cyclonic eddy originated in a southward meander of the KE front
around 158°E and pinched off southward from the meander in September
2011. Then the eddy moved westward and reached 151°E in January 2012.
Similar to the relatively high activity at the station located near the
center of the southward meander of the KE at 148°E (A in Figure 1b), the cyclonic eddy probably consisted of denser waters with a higher activity of 134Cs, because the surface 134Cs activity in the source area (the transition area) was more than 50 Bq m−3 in October 201129.
A model simulation has indicated that a cyclonic eddy detached from the
KE front holds the transition area water in it, while small leakage
occurs from layers denser than 26.0 σθ45.
Although the vertical profiles of temperature and salinity do not
indicate the presence of a cyclonic eddy between 32°N and 34°N (Figs. 3b and 3c), a small amount of leakage of 134Cs from such an eddy could explain the deeper penetration of the 134Cs (Figure 3a).
Alternatively, the deeper penetration can be attributed to direct
advection along subsurface isopycnals from the transition area. A
salinity minimum observed just south of the KE has been explained by
intrusion of Oyashio low-salinity water in the transition area; this
intrusion was associated with the frontal wave structure of the KE46, 47. The deeper 134Cs penetration just south of the KE (Figure 3a) implies that a similar subsurface intrusion occurred in the winter of 2012.
In the winter of 2012 the areal inventory of 134Cs (decay-corrected to the date of the accident) in the subtropical region (20°N–35°N) was estimated to be 1.6 ± 0.1 kBq m−2, which is about one-third of the areal inventory in the transition area (35°N–40°N), 4.6 ± 0.3 kBq m−2 (Figure 4). The integral of the areal inventory along the meridian in the subtropical region, however, was 2.7 ± 0.1 GBq m−1, which was about twice the value of the integral in the transition area, 1.4 ± 0.1 GBq m−1. The large inventory in the subtropical region suggests that the 134Cs
released from the FNPP1 had been transported not only eastward but also
southward. The average activity of the decay-corrected 134Cs in the STMW was 5.6 ± 0.4 Bq m−3.
We here assumed that this average activity could be regarded as the
mean activity of the whole STMW in the North Pacific, because our
observational line was located near the center of the area of STMW (Figure 5). An estimation of the total volume of STMW (about 1 × 106 km3)44 implies that the STMW contained about 6 PBq of 134Cs. Estimates of the total 134Cs
released to the North Pacific Ocean ranged from 10 PBq (direct
discharge of 4 PBq + atmospheric deposition 6 PBq) to 46 PBq (16 + 30
PBq). Thus, the 6 PBq inventory accounts for 10–60% of the total
release. However, the total inventory in the subtropical region derived
from the activity in STMW may be underestimated, because CMW probably
carried the radiocesium into the subtropical region, too (Figure 5).
In
this study we reconstructed the temporal change in Fukushima-derived
radiocesium in surface water of the western North Pacific during about
one year and a half after the accident. In April–May 2011 the 134Cs activity between 30°N and 40°N arose from the atmospheric deposition (Figure 2). In the north of the KE front, the transition area and subarctic region the discharged 134Cs was added while in the south of the KE front the atmospheric-deposited 134Cs was flushed out by the KE current during the following period. We found the subsurface maximum of 134Cs
in the subtropical region about 10 months after the accident. The
radiocesium that entered the ocean just south of the KE front via
atmospheric deposition was subducted southward immediately because of
formation of STMW. This process is reminiscent of the southward
spreading of radiocesium derived from the nuclear bomb testing in the
North Pacific via STMW formation48.
In addition, there is an indication that the Fukushima-derived
radiocesium in the transition area was conveyed southward across the KE
by cyclonic eddies that detached from the KE and by subsurface intrusion
under the KE. The rapid southward spreading of the 134Cs through subsurface layers seems to not have been simulated well in ocean models13, 15, 16, 32, 33,
probably because of problems associated with the simulation of
processes responsible for formation/subduction of STMW in these models.
The estimated inventory in the subtropical region (6 PBq or 10–60% of
the total inventory) is probably a lower limit of estimation because
contribution of CMW was not counted. The results in this study clearly
suggest that radiocesium released from FNPP1 into the North Pacific
Ocean had been transported not only eastward along with the surface
currents but also southward due to formation/subduction of STMW within
about 10 months after the accident.

Seawater sampling

Seawater samples for radiocesium
measurements were collected during a cruise of the Research Vessel MIRAI
(MR11-08) from December 2011 to February 2012. This cruise also served
as a repeat hydrography along one of observation lines of the World
Ocean Circulation Experiment (WOCE) in the western Pacific Ocean,
specifically the WOCE-P10/P10N line, which follows the 149°E meridian
approximately. We collected seawater at 31 stations along the line
between 10°N and 42°N (Figure 1).
Surface samples were taken from the deck with a bucket or by pumping
water from directly beneath the ship (a depth of about 4 m). The
temperature and salinity of the surface water in the bucket were
measured with a calibrated mercury thermometer and a salinometer
(Autosal model 8400, Guildline Instruments), respectively. The
temperature and salinity of the pumped water were measured with a sensor
system for conductivity (or salinity), temperature, and pressure
(SBE-11plus, Sea-Bird Electronics, Inc.). The salinity sensor on the
system was calibrated with bottled seawater, the salinity of which had
been measured with the salinometer. At 15 of the 31 stations, deeper
seawater from depths of 25 to 800 m was collected with 12-liter,
polyvinyl chloride bottles (Model 1010X NISKIN-X, General Oceanics,
Inc.) equipped with another sensor system (SBE-11plus, Sea-Bird
Electronics, Inc.). We collected about 20 dm3 of seawater
from each depth. The seawater was filtered through a 0.45 μm pore size
membrane filter (HAWP14250, Millipore) and acidified on board by adding
40 cm3 of concentrated nitric acid (Nitric Acid 70% AR, RCI Labscan, Ltd.) within 24 h after sampling.

Sample preparation

After
the cruise, radiocesium in the seawater sample was concentrated on
ammonium phosphomolybdate (AMP) in onshore laboratories for measurement
of gamma-ray activity. The sample preparation was conducted in
laboratories of four agencies: the Japan Agency for Marine-Earth Science
and Technology (JAMSTEC), the General Environmental Technos Co., Ltd.
(KANSO), the Japan Marine Science Foundation (JMSF), and the National
Institute of Radiological Sciences (NIRS). In the former two
laboratories, the pH of the seawater sample was adjusted to 1.6, and
0.26 (or 0.39) g of cesium chloride (>98.0%, KANTO Chemical Co.,
Inc.) was added to the seawater as a carrier. Then 4 (or 6) g of AMP,
made from hexaammonium heptamolybdate tetrahydrate (>98.0%, KANTO
Chemical Co., Inc.) and phosphoric acid (85%, Wako Pure Chemical
Industries, Ltd.), was added to the seawater and mixed well for two
hours to form an AMP/Cs compound. The compound was stored overnight and
then filtered onto a paper filter (Quantitative Filters Papers 5C, Tokyo
Roshi Kaisha, Ltd.). After drying at room temperature, the compound on
the filter was transferred to a teflon tube (5 cm3) for
gamma-ray measurement. The recovery of radiocesium from the seawater
into the AMP/Cs compound in the tube was estimated to be about 95%.
These procedures basically follow a protocol described in the literature49. The JMSF and NIRS laboratories used similar AMP methods50, 51. The recoveries of radiocesium at the JMSF and NIRS laboratories were about 95 and 91%, respectively.

Analyses

The
radiocesium activity in the AMP/Cs compound was measured in the
laboratories of the Mutsu Oceanographic Institute/JAMSTEC, Low Level
Radioactivity Laboratory/Kanazawa University (LLRL/KU), and the NIRS. In
JAMSTEC, the radiocesium was measured with low-background Ge-detectors
(Well-type GCW2022-7915-30-ULB, Canberra Industries, Inc.), which were
calibrated with gamma-ray volume sources (Eckert & Ziegler Isotope
Products) certificated by Deutscher Kalibrierdienst (DKD). The gamma
counting time ranged from a day to a week, and 134Cs and 137Cs
activities were evaluated from gamma-ray peaks at 605 and 661 keV,
respectively. The averages of the detection limits (3 standard
deviations) of the 134Cs and 137Cs measurements were calculated to be 0.53 and 0.20 Bq m−3, respectively. In the case of the 605 keV photopeak from 134Cs,
the cascade summing effect was corrected. The factor for the summing
effect was about 2, which was calculated as the difference between the 134Cs/137Cs
ratios at a distance of 15 cm from the detector and in the well hole of
the detector. The averages of the analytical uncertainties (standard
deviations) for the 134Cs and 137Cs measurements
were calculated to be 13% and 7%, respectively. These uncertainties
arose from the gamma counting, the calibration, and the correction for
the summing effect. The radioactivity of 137Cs in a certified reference material for radionuclides, a water sample from Irish Sea (IAEA-443)52, was measured in the JAMSTEC laboratory. Results (0.36 ± 0.02 Bq kg−1, decay-corrected to 1 January 2007) agreed well with the radioactivity of 137Cs
in the certified seawater. The radiocesium activity was also measured
in the LLRL/KU laboratory with low-background Ge-detectors51, 53. The averages of the detection limits for the 134Cs and 137Cs measurements in the LLRL/KU laboratory were 0.16 and 0.05 Bq m−3, respectively. The averages of the analytical uncertainties for 134Cs and 137Cs
were calculated to be 11 and 6%, respectively. In the NIRS laboratory,
the radiocesium activity was measured with Ge-detectors (GX-2019,
Canberra Industries, Inc.). The uncertainties of radiocesium
measurements in the NIRS laboratory (14% and 6% for 134Cs and 137Cs, respectively) were nearly equal to those in the JAMSTEC and LLRL/KU laboratories. The detection limits (2.2 Bq m−3 and 1.4 Bq m−3 for 134Cs and 137Cs, respectively), however, were higher than those in the JAMSTEC and LLRL/KU laboratories. Measurements of 134Cs and 137Cs
activities in AMP/Cs compounds derived from certified reference
materials (IAEA-443 and 445), which were prepared by KANSO, among the
three laboratories resulted in good agreement within uncertainties. This
agreement confirmed the comparability of the radiocesium measurements
at the three laboratories.

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